Genesis of geothermal water in the Laochang area, eastern Yunnan Province: Constraints from hydrochemistry and C-H-O-S isotopes
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摘要:
滇东弥勒-师宗断裂带地热资源丰富，但是由于研究程度较低，成因机制不明，制约了区内地热资源的可持续开发利用。本文以弥勒-师宗断裂带北段老厂地区天然温泉水和地热钻孔水为研究对象，综合应用野外调查、水文地球化学和环境同位素方法，对区内地热水的地球化学特征和成因机制进行了研究。结果显示，区内地热水pH值介于7.30～8.12之间，TDS在224～382 mg/L之间，属于弱碱性淡水。地热水水化学类型为HCO3·SO4-Ca型和HCO3·SO4-Ca·Na型，且含有较高含量的Fe、As、Sb等微量组分，不宜饮用。地热水中HCO3−的δ13C值为−3.31‰～−7.79‰，计算得出参与水岩作用的CO2的δ13C值为−9.50‰～−15.68‰，具有明显的沉积有机质来源特征。离子比值分析及硫同位素特征表明碳酸盐岩矿物和石膏的溶解是区内地热水主要离子来源的控制因素，此外赋存于浅部断裂带内的硫化物矿体氧化以及阳离子交换作用对地热水水化学组分产生了一定的影响。氢氧同位素特征及14C测年结果表明区内地热水的补给来源为晚更新世时期温度较低的大气降水，补给高程为
1984.9 ～2283.9 m，补给区位于研究区周边的山区。硅焓方程计算的冷水混合比例为71.9%～82.4%，综合硅焓方程计算的热储温度和校正后的石英地热温标计算的热储温度，认为区内地热水的热储温度为87.5～135.7℃，地热水循环深度为1538.0 ～2502.0 m。研究结果有助于提升滇东弥勒-师宗低温热水带地热水成因研究水平，为区内地热资源的合理开发及保护提供理论支撑。Abstract:The Mile-Shizong Fault Zone in Eastern Yunnan is rich in geothermal resources. However, due to the less research and unclear genetic mechanism, the sustainable development and utilization of geothermal resources in the region has been restricted. Taking the hot spring water and geothermal well water in Laochang area in the north section of the Mile-Shizong Fault Zone as the research object, this paper comprehensively applies the integration of field investigation, hydrogeochemistry and environmental isotope to study the characteristics and genetic mechanism of geothermal water in the study area. The pH values of the geothermal water are between 7.30～8.12 and TDS values are between 224～382 mg/L, which belongs to weakly alkaline fresh water. The hydrochemical types of geothermal water are HCO3·SO4－Ca type and HCO3·SO4－Ca·Na type. The geothermal water contains high contents of trace components such as Fe, As and Sb, and thus are not suitable for drinking. The δ13C value of HCO3− is between −3.31‰ and −7.79‰, and the calculated δ13C value of CO2 involved in water-rock reaction is between −9.50‰ and −15.68‰, which is mainly from sedimentary organic matter. Ion ratio analysis and sulfur isotope characteristics show that the dissolution of carbonate minerals and gypsum is the main factor controlling ion concentrations of geothermal water. In addition, the oxidation and cation exchange of sulfide ore bodies in the fault zone have a certain impact on the composition of geothermal water. Hydrogen and oxygen isotope characteristic and 14C dating results show that the recharge origin of the geothermal water is the atmospheric precipitation with low temperature in the late Pleistocene, and the supply elevation is between
1984.9 m and2283.9 m. The recharge area is located in the mountainous area with the elevation of1984.9 ～2283.9 m around the study area. The mixing ratio of cold water calculated by silicon enthalpy equation is between 71.9% and 82.4%. The heat reservoir temperature calculated by silicon enthalpy equation and corrected quartz geothermal temperature scale is between 87.5℃ and 135.7℃. The circulation depth of geothermal water is between1538.0 m and2502.0 m. The research results are helpful to improve the research level of geothermal water genesis in the Mile-Shizong low-temperature hot water zone in Eastern Yunnan, and provide theoretical support for the rational development and protection of geothermal resources in the area.-
Key words:
- Laochang area /
- Mile-Shizong Fault Zone /
- Geothermal water /
- Hydrochemistry /
- C-H-O-S isotope
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表 1 研究区地热点出露概况
Table 1. General situation of geothermal waters in the study area
名称 编号 地貌形态 出露高程（m） 温度（℃） 构造部位 温泉出露的地层及
钻孔揭露的地层大河沟温泉 WQ01 出露于老厂河河谷右侧 1840.9 25.0 背斜扬起端的断裂带附近 二叠系茅口组（P1m）灰岩、白云质灰岩 WQ02 出露于老厂河河谷左侧 1840.9 28.1 背斜扬起端的断裂带附近 二叠系茅口组（P1m）灰岩、白云质灰岩 大旧克钻孔 ZK01 人工钻孔揭露于大旧克斜坡地带，孔深500 m。 1747.0 47.0 背斜倾伏端的断裂带附近 二叠系茅口组（P1m）灰岩、白云质灰岩 丕德村钻孔 ZK02 人工钻孔揭露于丕德河阶地，孔深600 m。 1448.0 43.5 背斜倾伏端的断裂带附近 二叠系茅口组（P1m）灰岩、白云质灰岩 阿文村钻孔 ZK03 人工钻孔揭露于各布厂小河阶地，孔深200 m。 1841.0 32.5 背斜倾伏端的断裂带附近 二叠系茅口组（P1m）灰岩、白云质灰岩 
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表 2 研究区水化学组成
Table 2. Chemical composition of water in the study area
样号 pH TDS Na+ K+ Ca2+ Mg2+ HCO3− SO42− Cl− H2SiO3 Sr F Fe As Sb 硫化物 mg/L WQ01 7.30 306 12.68 0.66 81.92 8.55 160.78 112.00 1.95 12.86 0.23 0.55 0.21 0.007 0.002 0.005 WQ02 7.58 382 26.00 2.19 82.81 14.96 154.48 166.00 3.85 15.80 0.52 0.66 3.30 0.013 0.002 0.005 ZK01 7.84 246 2.39 1.13 63.43 9.62 126.10 80.80 0.77 35.93 1.19 2.12 0.25 0.062 0.021 0.068 ZK02 8.12 224 22.51 1.26 47.57 8.55 154.48 57.10 0.58 36.38 0.91 3.03 0.61 0.082 0.011 0.136 ZK03 7.91 234 1.79 0.48 68.71 7.48 113.49 99.90 0.52 20.55 0.46 1.15 0.18 0.032 0.039 0.051 DL01 7.56 148 2.09 0.54 46.38 3.13 138.65 20.73 0.58 9.32 0.11 0.44 0.13 0.239 0.014 0.005
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表 3 研究区地热水稳定同位素及相应的计算结果
Table 3. isotopic compositions of the geothermal water in the study area and its corresponding calculation results
样号 δ13C/‰ δD/‰ δ18O/‰ δ34S/‰ 补给高程/m 补给区温度/℃ 计算的δ13CCO2/‰ 式1 式2 平均值 式1 式2 平均值 WQ01 −7.79 −78.26 −11.23 / 1970.6 1999.2 1984.9 5.4 2.2 3.8 −15.68 WQ02 −6.39 −78.39 −11.25 0.19 1976.1 2004.7 1990.4 5.6 2.3 3.9 −13.72 ZK01 −3.31 −85.32 −12.15 16.55 2269.6 2298.2 2283.9 6.4 3.7 5.1 −9.50 ZK02 −4.31 −85.15 −12.07 17.44 2262.7 2291.3 2277.0 6.8 4.0 5.4 −10.74 ZK03 −6.67 −80.86 −11.62 0.50 2080.8 2109.4 2095.1 7.2 4.6 5.9 −13.91 DL01 −7.06 −79.88 −11.42 −3.00 2039.2 2067.8 2053.5 7.1 4.5 5.8 −15.72
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表 4 研究区地热水主要矿物饱和指数
Table 4. Main mineral saturation index of the geothermal water in the study area
样号 硬石膏 文石 方解石 白云石 萤石 岩盐 石膏 天青石 石英 玉髓 无定型SiO2 Fe(OH)3 WQ01 −1.71 −0.22 −0.08 −0.81 −1.47 −9.18 −1.49 −2.33 0.21 −0.23 −1.07 2.12 WQ02 −1.57 0.05 0.20 0.02 −1.39 −8.59 −1.36 −1.84 0.24 −1.01 −1.01 3.16 ZK01 −1.79 0.42 0.54 0.76 −0.62 −10.35 −1.70 −1.66 0.33 −0.80 −0.80 0.99 ZK02 −2.07 0.61 0.74 1.23 −0.39 −9.49 −1.95 −1.91 0.38 −0.78 −0.78 1.53 ZK03 −1.77 0.28 0.42 0.29 −0.97 −10.62 −1.58 −2.03 0.29 −0.12 −0.93 1.66 DL01 −2.57 −0.33 −0.18 −1.31 −1.69 −10.45 −2.32 −3.25 0.20 −0.26 −1.13 2.49
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表 5 研究区地热水热储温度估算结果
Table 5. Estimated temperature of the geothermal reservoir of the geothermal water in the study area
样号 SiO2含量
/mg·L−1SiO2温标热储
温度（校正前）/℃冷热水
混合比/%SiO2含量
（校正后）/mg·L−1SiO2温标热储温
度（校正后）/℃硅焓方程
热储温度/℃热储温度
平均值/℃WQ02 12.16 45.7 82.4 35.5 86.5 88.6 87.5 ZK01 27.63 76.1 71.9 80.0 125.1 125.0 125.0 ZK02 27.98 76.6 76.6 96.1 135.0 136.4 135.7 ZK03 15.81 54.8 80.6 51.7 103.4 103.6 103.5
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表 6 研究区地热水3H、14C测试分析结果
Table 6. Analytical results of 3H and 14C for the geothermal water in the study area
样品 3H/TU 14C浓度/pmc 表观年龄/ka Pearson模型
校正年龄/kaZK01 ＜1.0 4.50 25.64 14.13 ZK02 ＜1.0 4.03 26.55 16.22
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